Geological Quarterly, 2004, 48 (4): 309–316

New Late Vendian palaeogeography of and the TESZ

Jerzy NAWROCKI, Andrej BOGUCKIJ and Valentas KATINAS

Nawrocki J., Boguckij A. and Katinas V. (2004) — New Late Vendian palaeogeography of Baltica and the TESZ. Geol. Quart., 48 (4): 309–316. Warszawa.

New palaeomagnetic poles obtained from the Vendian tuffs and basalts of western Ukraine indicate the necessity of a substantial revision of the Late Vendian–Early Cambrian palaeogeography of the Baltic plate. The palaeopole calculated for the most stable component iso- lated from the Vendian tuffs and basalts is far away from the Vendian–Cambrian apparent polar wander path (APWP), constructed on the basis of Scandinavian poles but is very close to the pole recently isolated from the Vendian sediments of the White Sea Region. Depend- ing on the polarity of the newly-determined Late Vendian pole, two palaeogeographic models of the Baltic plate in the Late Vendian–Early Cambrian are possible. In our preferred model the Baltic plate moved at that time from the moderate southern latitudes to the equator rotating anticlockwise of ca. 120o. This reconstruction explains the geological structures of the marginal zones of Baltica better than the previously proposed stationary model of the Late Vendian–Cambrian Baltica. According to the new late Vendian palaeogeographic scenario, the European, passive margin of Baltica was separated from an active, Avalonian margin of Gondwana. The Late Neoproterozoic tectonic structures of the Brunovistulian and the Ma³opolska Block were developed near the present day southwestern corner of Baltica that was tectonically active at that time. Alternative reconstruction shows the Baltic plate moving from the moderate northern latitudes in the Vendian, crossing palaeoequator in the latest Vendian, and reaching moderate southern palaeolatitudes in the Late Cambrian. This model, however, would have required exceptionally high plate velocity (ca. 33 cm/year).

Jerzy Nawrocki, Polish Geological Institute, Rakowiecka 4, PL-00-975 Warszawa, Poland; e-mail: [email protected]; Andrej Boguckij, Deptartment of Geography, Lvov University, Doroszenki 41, 290000 Lvov, Ukraine; Valentas Katinas, Institute of Geology and Geography, žev¹enkos St. 13, LT-2600 Vilnius, Lithuania (received: July 7, 2004; accepted: November 3, 2004).

Key words: Baltica, Ma³opolska, Brunovistulian, Vendian, palaeogeography, palaeomagnetism.

INTRODUCTION ern Poland, this domain consists of at least three fault-bounded crustal units. From the margin of Baltica outwards, these are the £ysogóry, the Ma³opolska and the Brunovistulian (Fig. 1). The Brunovistulian was one of the first tectonic units of Central Eu- Since the new palaeomagnetic poles for 535 and 500 Ma rope to be defined as a “terrane” (Brochwicz-Lewiñski et al., were reported, the drift history of Baltica in the Late 1986) and still remains the best-documented terrane of the cen- Vendian–Cambrian has appeared to be well recognized tral part of TESZ (Po¿aryski, 1991; Dadlez, 1995; Franke, (Torsvik and Rehnström, 2001). On the basis of this data and 1995; Pharaoh, 1999). The basement of this terrane is com- the Vendian palaeopoles from the Fen complex (Piper, 1988; posed of metamorphic and igneous rocks, mostly Cadomian Meert et al., 1998), only a minor mobility of the Baltic plate for (Neoproterozoic) in age (Dudek, 1980; Van Breemen et al., 555 to 500 Ma timespan has been proposed (e.g. Hartz and 1982; Finger et al., 2000; ¯elaŸniewicz et al., 2001). In some Torsvik, 2002). In the reconstruction by Hartz and Torsvik places they are covered by the Vendian flysh sequences meta- (2002), Baltica is located between 30° and 60° of southern lati- morphosed in a greenschist grade (¯elaŸniewicz et al., 2001). tude, with its present SW edge facing to the north. This model The Late Vendian metamorphosed flysh sequences cover also does not explain, however, some tectonic problems like the the Ma³opolska Tectonic Block (¯elaŸniewicz, 1998). Because presence of a Cadomian orogen in the basement of the tectonic of these orogenic features, it is difficult to accept any blocks situated near the present SW edge of Baltica. Neoprotorozoic palaeogeography with the Ma³opolska and The present SW margin of Baltica is bordered by a crustal Brunovistulian in the passive margin of Baltica as is presented domain, named the Trans-European Suture Zone (TESZ), by Hartz and Torsvik (2002). Lewandowski (1993) locates the which separates the Precambrian crust of this plate from the Ma³opolska Block near the present southern margin of Baltica Variscan and Alpine mobile belts of western Europe. In South- 310 Jerzy Nawrocki, Andrej Boguckij and Valentas Katinas

A certain modification of Baltica palaeogeography has been recently proposed by Lewandowski and Abrahamsen (2003), who situated this continent in the more equatorial posi- tion in the Early Cambrian. New palaeomagnetic studies con- cerning the Vendian sediments of White Sea Region (Popov et al., 2002) disclosed a new palaeopole that is not concordant with the coeval Scandinavian palaeopoles. Any new palaeo- magnetic pole may, therefore, potentially clarify the problem of palaeogeography of Baltica at the turn of the Vendian and Cambrian. For this reason we decided to undertake a palaeo- magnetic study of Late Vendian and Early Cambrian rocks from Ukraine and Estonia.

NEW PALAEOMAGNETIC RESULTS

MATERIAL AND METHODS

Two exposures of the Vendian extrusives from the Volhynia region of the Western Ukraine were sampled for palaeomagnetic investigations. The samples were drilled from the doleritic parts of two lava flows of the pillar basalts croping out in the Bazaltovoye-5 quarry (25 samples), and from dolerit- ic parts of the layered basalts and underlaing tuffs in the Rafalivka quarry (35 samples, see Fig. 1). Sampling was con- strained to three lava flows and one layer of tuffs. All sampled rocks are attributed to the Ratno Beds that compose the upper- most part of the volcanogenic Volhynian Series (Bia³owolska et al., 2002). The Ratno Beds extend as far as SE Poland, where they form uppermost part of the S³awatycze Series (a counter- part of the Volhynian Series). Compston et al. (1995) obtained U-Pb age of 551 ± 4 Ma from the uppermost tuffs of the S³awatycze Series (Fig. 1B). Hence, basalts and tuffs from Bazaltovoye-5 and Rafalivka should be very close to this age. It is unlikely that they are much older than 551 Ma. The Lower Cambrian red mudstones of the Baltija Group were sampled in Kunda quarry (NE Estonia), where 15 hand samples were taken. These rocks are correlated with the Manykayan stage (Paskievicius, 1997). The Vendian sediment, adjanced to the studied Volhynian intrusives dips 3° to the west. The Lower Cambrian sediments from Kunda quarry dip 2° to SW. Vendian samples were subjected to both alternating field (AF) and thermal demagnetization experiments. For Early Cambrian red beds we used thermal demagnetization only. De- Fig. 1. A — location of the studied outcrops within a tectonic sketch map of magnetization results were analysed using orthogonal vector the Central Europe (CDF — Caledonian deformation front, PTB — plots (Zijderveld, 1967), and the directions of the linear seg- Pomerania Tectonic Block, LTB — £ysogóry Tectonic Block, MTB — Ma³opolska Tectonic Block, BVT — Brunovistulian Terrane); B — strati- ments were calculated using principal component analysis graphic subdivision of Vendian–Cambrian sediments from the (Kirschvink, 1980). Magnetic mineralogy was determined with Lublin–Volhyn part of the (after Poprawa and the use of isothermal remanent magnetization (IRM) Paczeœna, 2002); location of studied exposures Bazaltovoye-5 and techniques and thermomagnetic analyses. Rafalivka is marked with circles in the Early Palaeozoic. He postulates a large-scale tectonic RESULTS OF DEMAGNETIZATION transport of the Ma³opolska to its present position during the Variscan . However, the palaeomagnetic pole obtained Most of the samples from the Volhynia revealed a from the Bardo diabase (S part of the Holy Cross Mts., low-coercivity natural remanent magnetization (NRM) compo- Ma³opolska Block) indicates that such a movement could not nent, removed by alternating fields up to 20 mT and tempera- take place after the Silurian (Nawrocki, 2000). tures of about 350°C (Fig. 2). In the samples from Rafalivka this component was strongly dispersed and therefore was not New Late Vendian palaeogeography of Baltica and the TESZ 311

Fig. 2. Typical demagnetization characteris- tics (orthogonal plots, intensity decay curves and demagnetization directional tracks) of Vendian basalts and tuffs from Rafalivka and Bazaltovoye-5 quarries, and Lower Cam- brian mudstones from Kunda quarry Circles in the orthogonal plots represent ver- tical projections, squares represent horizontal projections; the characteristic components “A”, “B”, “C1” and “C2” are marked on the orthogonal plots; Irm — intensity of remanent magnetization, Inrm — initial in- tensity of natural remanent magnetization

intesity, “B” magnetization usually fluctuated at the last levels of demag- netization. Samples from the Lower Cam- brian red mudstones revealed the presence of a one distinct component “C2”. This magnetization was de- finedintemperaturesupto550°C, as a straight-line segment not directed towards the origin in orthogonal pro- jection (Fig. 2). These rocks also con- tained a high temperature compo- nent. Its credible definition was im- possible because of a substantial in- crease of the magnetic susceptibility at temperatures higher than 550°C.

MAGNETIC CARRIERS

IRM experiments and the subse- quent thermal demagnetization of the saturation magnetization confirm the predominance of magnetic carriers from an ulvospinel-magnetite solid evaluated statistically. Samples from Bazaltowoye-5 contained solution series in the basaltic samples (Fig. 4). The structure of a very large low-coercivity component “C1” (Fig. 2). This NRM indicates the presence of two magnetic phases, differing in quickly removed component is not well documented because coercivity and unblocking temperatures. Thermal and AF de- the number of demagnetization levels was not sufficient. Nev- magnetization of NRM indicate that the “A” component is car- ertheless, the directions defined for particular samples by the ried by moderately high-coercivity minerals with unblocking best-fitted lines group in the first quarter of the hemisphere temperature of about 570°C(Fig. 2). This demagnetization be- (Fig. 3). After the removal of the low-coercivity overprint haviour is typical for basaltic lava containing deuterically-oxi- above 20 mT or 350°C, a high-coercivity component “A” with dised titanomagnetite (e.g. Buchan and Halls, 1990). The com- unblocking temperatures of about 570°C can be identified in ponent “B” is carried by a medium-coercivity mineral with un- the samples from tuffs and basalts of Rafalivka quarry. The blocking temperature of about 450°C, most probably “A” magnetization is isolated as a straight-line segment di- titanomagnetite. The component “C1” could be recorded by rected towards the origin in an orthogonal projection. maghemite because of its unblocking temperature of about In the samples from Bazaltowoye-5, a second component 350°C and a certain decrease of magnetic susceptibility at tem- was also isolated. This component defined as “B”, was demag- peratures 350–450°C, caused by a mineral transformation from netized in the field of about 80 mT and temperatures not ex- maghemite into hematite. A mineral with unblocking tempera- ceeding 450°C (Figs. 2 and 3). It is poorly documented in par- ture of about 550°C, such as magnetite is a carrier of component ticular samples because of a very large overprint of “C1” com- “C2”, isolated from the Cambrian red beds. IRM experiment in- ponent. Associated with no more than 2% of initial NRM dicates also the presence of hematite in these rocks (Fig.4). 312 Jerzy Nawrocki, Andrej Boguckij and Valentas Katinas

Fig. 3. a — stereographic projections of line-fit palaeo- magnetic directions from the studied Vendian and Early Cambrian rocks; open (closed) symbols denote upward (downward) pointing inclinations; the stereographic plots are presented in tilt-corrected coordinates; b — table with char- acteristic directions and palaeopoles isolated from Vendian basalts and tuffs of Volhynia and Early Cambrian mudstones from Estonia; N — number of samples used in calculations, D/I — declination/inclination, K — precision parameter (after

Fisher, 1953), a95— semi-angle of the cone of 95% confi- dence, Plat. — latitude of south palaeomagnetic pole, Plong. — longitude of south palaeomagnetic pole, dp — error of the distance between site and palaeopole, dm — palaeodeclination error

palaeopole from the White Sea Region (Popov et al., 2002). It should be stressed, however, that compo- nent “A” has about 40° higher value of inclination than “B” component. Hence, they cannot be coeval. The component (and palaeopole) “A” is most proba- bly nearly primary connected with the emplacement of tuffs and basalts (c. 560–550 Ma ago). It is carried by a fine-grained DISCUSSION magnetite that was demagnetized only in a high amplitude al- ternating field and moderate to high temperatures. Much more PALAEOMAGNETIC DATA lower values of unblocking temperatures and coercivites of “B” component can indicate its secondary origin. It may be The directions were converted into the palaeomagnetic linked with the migration of post-magmatic brines along the poles that were compared with the apparent polar wander path pillar structures of basalts. However, “B” palaeopole does not (APWP) for Baltica (Fig. 5). “A” and “B” palaeopoles are far correspond to the post-Vendian part of the Baltic APWP away from the Late Vendian–Cambrian segment of the path (Fig. 5) being located between the palaeopole from the White constructed on the basis of Scandinavian poles (see Torsvik Sea Region (Popov et al., 2002) and the Early Cambrian and Rehnström, 2001). They correspond to the Late Vendian palaeopole from the Nekso Formation (Lewandowski and Abrahamsen, 2003). Because of this, it should be also considered as a Late Vendian one, being, however, younger than “A” palaeopole and secondary in origin. Due to insufficient documenta- tion, “B” palaeopole was not consid- ered in the construction of a revised APWP for Baltica. The modified Late Vendian-Early Cambrian APWP for Baltica (Fig. 5)is basedontheassumptionthat“A” component is of reversed polarity. Normal polarity is assigned to a char- acteristic component isolated from the Nekso sandstones (Lewandowski and Abrahamsen, 2003). The polarity of the direction from the White Sea Re- gion is regarded as opposite to that as- sumed by Popov et al. (2002). Our re- sults make APWP for Baltica much longer in the time concerned than that proposed by Torsvik and Rehnström (2001). Palaeomagnetic poles from the Volhynia and White Sea Region are far away from the palaeopoles isolated from the Fen complex (Piper, 1988; Fig. 4. a — thermal demagnetization of orthogonal-axis IRM curves obtained for tuffs and basalts from Meert et al., 1998). It should be Rafalivka and Bazaltovoye-5; b — IRM acquisition curves prepared for the same samples and for the Lower Cambrian mudstone from Kunda quarry stressed, however, that the Fen com- New Late Vendian palaeogeography of Baltica and the TESZ 313

Fig. 5. Southern APWP for Baltica (thick grey line) and selected palaeopoles obtained from Vendian–Cambrian rocks of Baltica. The Late Cambrian–Ordovician segment of the path is presented after Torsvik et al. (1990, 1996) and Torsvik and Rehnström (2001). Three other versions of the Late Vendian–Early Cambrian segment of the Baltic APWP are also presented. The thin black line demonstrates the version according to Popov et al. (2002), the thin broken line — according to Torsvik and Rehnstrom (2001) and the thick broken line has been drawn according to Lewandowski and Abrahamsen (2003). 1 — palaeopole “A” from Rafalivka (this paper), 2 — palaeopole from Vendian sediments of White Sea Region (Popov et al., 2002), 3— palaeopole “B” from Bazaltovoye-5 (this paper), 4 — palaeopole from the Lower Cambrian red beds of the Brunovistulian Terrane (Nawrocki et al., 2004), 5 — palaepole from Nekso Formation (Lewandowski and Abrahamsen, 2003), 6 — palaeopole from Fen Complex (Meert et al., 1998), 7 and 8 — palaeopoles from Tronetrask Formation and Alum Shale respectively (Torsvik and Rehnström, 2001), 9 — palaeopole “C1” from Bazaltovoye-5 (this pa- per), 10— palaeopole “C2” from Kunda (this paper). In the construction of the Late Vendian segment of the new Baltic APWP the palaeopoles number 1 and 2 were used only. The poorly-documented palaeopole num- ber 3 was not taken into consideration

plex is most probably older than the Volhynian basalts. Its age Terrane (¯elaŸniewicz, 1998; Finger et al., 2000) can be justi- was estimated to be 568–598 Ma (Meert et al., 1998). The fied by the model of the Late Vendian Baltica “X”. In this re- palaeopole “C1” is convergent with the Cambrian segment of construction, the present-day SW margin of Baltica was sepa- the Baltic APWP. The palaeopole “C2” corresponds to its Late rated from the Neoproterozoic structures of the Avalonian parts Cambrian/Early Ordovician part (Fig. 5). This indicates their of peri-Gondwana (Fig. 6B). The present-day southern and secondary origin. Palaeomagnetic pole number 4 (Fig. 5), ob- eastern margins of this plate were tectonically active during its tained from the Early Cambrian red beds of the Brunovistulian drift to nearly equatorial position in the Late Vendian–Early Terrane (Nawrocki et al., 2004) corresponds to the area of Cambrian. The Baltoscandian margin of Baltica was passive at stereonet with the Late Vendian poles number 1, 2 and 3. This that time. This interpretation is in agreement with the existing departure of pole number 4 from the Early Cambrian segment geological evidence (see e.g. Svenningsen, 1995; Poprawa et of the new APWP can be explained (see next chapter) by a sig- al., 1999; Willner et al., 2001; Scarrow et al., 2001; Roberts and Siedlecka, 2002; Kalvoda et al., 2002, 2003; Jaworowski nificant (c. 80°) tectonic rotation of this terrane in the Early and Sikorska, 2003). Moreover, our reconstruction can also ex- Palaeozoic. plain why some detrital zircon grains from the Cambrian sedi- ments of the present SW slope of Baltica have Cadomian ages NEW LATE VENDIAN-CAMBRIAN PALAEOGEOGRAPHY (Valverde-Vaquero et al., 2000). OF BALTICA AND THE TESZ AREA The Neoproterozoic orogenic sequence of the Bruno- vistulian terrane was developed in the peri-Gondwana area. Since an unequivocal polarity interpretation of This terrane was separated from the Avalonian part of palaeomagnetic directions from Volhynia and White Sea Re- peri-Gonwana together with Baltica in the Late Vendian. The gion is not possible, two versions of palaeogeographic recon- youngest Neoproterozoic structures of the Brunovistulian struction of Baltica in the Late Vendian–Early Cambrian Terrane were developed when this unit was located near a tec- should be discussed (Fig. 6A). Model “X”, which we prefer, tonically active, present-day SW corner of Baltica. The corresponds to the modified Late Vendian-Early Cambrian Grenvilian Nd model ages and the same age of single zircon APWP for Baltica (Fig. 5). It presents the Baltic plate moving grains from the basement of Brunovistulian (Finger et al., at that time from moderate southern latitudes to the equator and 2000; Hegner and Kröner, 2000) can be explained if this unit rotating anticlockwise of ca. 120°. This model, apart from a fast had been located in the proximity of the Avalonian and south (ca. 16 cm/year) plate drift, needs a relatively high rotation rate American margin of Gondwana. Cambrian trilobite fauna from (c. 6°/Ma). Alternative reconstruction of Baltica presented as the Brunovistulian Terrane, if diagnostic, indicate rather Baltic model “Y” (Fig. 6A) shows the Baltic plate moving from the links (Or³owski, 1985; Nawrocki et al., 2004). Early Cambrian Vendian position at moderately northern latitudes, crossing the palaeolatitude (ca.7°) obtained from palaeomagnetic studies palaeoequator in the latest Vendian and reaching moderate (Nawrocki et al., 2004) matches the Early Cambrian location of southern palaeolatitudes during the Cambrian (Fig. 6A). This the TESZ margin of Baltica or the Arabian part of peri-Gond- model, discussed by Nawrocki et al. (2004), would have re- wana. This second location of the Brunovistulian Terrane in the quired an exceptionallyhigh plate velocity (ca. 33 cm/year). Early Cambrian is rather impossible because of the Baltic links The existence, near the present eastern and southwestern of the trilobite fauna and the Grenvilian ages noted in its base- edges of Baltica, of crustal blocks containing a very distinct re- ment. The Brunovistulian Terrane was probably dextrally cord of the Neoproterozoic orogeny, like the Brunovistulian translated along the present day SW edge of Baltica while 314 Jerzy Nawrocki, Andrej Boguckij and Valentas Katinas

Fig. 6. A — palaeogeographic reconstruction of Baltica for the Late Vendian–Early Permian time span. The Early Ordovician–Early Perm- ian location is quoted after Torsvik et al. (1990, 1996). The Late Vendian–Late Cam- brian setting corresponds to palaeomagnetic poles and paths presented in Figure 5. Baltica “X” (grey in colour) has been drawn accord- ing to the new APWP presented in this paper. The white-coloured Baltica “Y” is in compli- ance with the APWP of Popov et al. (2002); B — simplified palaeogeographic reconstruc- tions showing Gondwana megacontinent (adopted from Torsvik and Rehnström (2001), Torsvik et al. (1996) and the position of the Baltica in the Late Vendian and Early Cam- brian; PR — Perunica, AV — , AR — Armorica, BVT, — Brunovistulian Terrane, MDB — Ma³opolska-Dobrogea Tec- tonic Block, PTB — Pomerania Tectonic Block. The nearly equatorial position of the Brunovistulian Terrane at ca. 540 Ma is pre- sented according to palaeomagnetic data of Nawrocki et al. (2004)

The palaeogeography of the Ma³opolska Block in the Late Vendian is not clear. This unit could form a marginal part of Baltica, being always located near its present position. Then the partly metamorphosed Late Vendian flysh sequences covering the Ma³opolska (¯elaŸniewicz, 1998) could be related to the collision of any Cadomian tectonic block with this part of Baltica. It should be stressed, how- ever, that this solution does not match the results of subsidence analysis where the Late Vendian–Cambrian ex- tension at the SW edge of Baltica is postulated (Poprawa et al., 1999). Be- cause of this, another setting of the Baltica rotated in the Late Vendian time. It should be stressed, Ma³opolska in the Late Vendian should be taken into consider- hovewer, that this terrane could not then reach its present posi- ation. This unit could form an external part of the area with the tion in the TESZ because the Cambrian palaeomagnetic pole Late Neoproterozoic deformations, occupying the active south- characteristic for this unit (Nawrocki et al., 2004), being ern margin of Baltica. It was moved as a proximal terrane to the strongly rotated, does not fit the Baltic APWP (Fig. 5). The fi- present position during the Late Vendian rotation of Baltica. nal stage of the tectonic transport of the Brunovistulian Terrane This model corresponds to the reconstructions proposed by in the vicinity of the Ma³opolska Block took place after the Lewandowski (1993) and Narkiewicz (2002). However, in our Ludlovian, but before the sedimentation of the Lower Devo- proposition, the time and source of the tectonic transport of nian sandstones of the “old red” type. The Ludlovian sediments Ma³opolska Block are different. of the Ma³opolska Block were not derived from the The geological structure, lithology and geochronology of Brunovistulian Terrane but from the island arc located west of the Brunovistulian Terrane show a broad fit with the crystalline the Ma³opolska, in the place occupied now by the basement of the Istanbul Zone (Kalvoda et al., 2002). The Brunovistulian Terrane (Koz³owski et al., 2004). The Early Vendian and Cambrian sequences of the central Ma³opolska Devonian proximity of the Brunovistulian and the Ma³opolska Block and Brunovistulian Terrane correlate well with the can be inferred from the distribution of the boundaries of par- Scythian Platform (Kalvoda et al., 2003). This supports our in- ticular “old red” facies (Pajchlowa and Mi³aczewski, 1974). terpretation, in which the Bunovistulian Terrane and the These boundaries cut the Kraków-Lubliniec fault zone that Ma³opolska Block could form, in the latest Vendian, a link be- separates both units. tween NW passive margin of Baltica and its active southern New Late Vendian palaeogeography of Baltica and the TESZ 315 sector where the Scythian Platform and the Istanbul Zone are Vendian and moved to the equator, meanwhile rotating located up till now. anticlockwise by ca. 120°. The new reconstruction of Baltica explains better the geo- logical framework of its marginal zones than the stationary CONCLUSIONS model previously proposed. The Late Neoproterozoic tectonic structures of the Brunovistulian Terrane and the Ma³opolska Block were developed near the present day SW corner of The palaeopole calculated for the most stable component Baltica, which was then tectonically active. isolated from the Vendian tuffs and basalts from Volhynia is far away from the Vendian–Cambrian APWP constructed on the Acknowledgments. We thank M. £anczont, K. Kirsimäe basis of Scandinavian poles, but is very close to the pole isolated and W. Matejuk for their in-field help. Comments by M. recently from the Vendian sediments of the White Sea Region. Lewandowski and R. Van der Voo led to substantial improve- According to the new palaeomagnetic data, two palaeo- ments of the manuscript. This is a contribution to the research geographic models for Baltica in the Late Vendian–Early project “Palaeozoic Accretion of Poland” (PCZ-07-21). Cambrian are proposed. In our prefered model, the Baltic plate occupied the moderate southern latitudes in the Late

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